A review on the analysis of aeromagnetic anomaly and its geological and tectonic applications
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摘要: 航磁异常在地质构造研究中具有覆盖广、成本低以及横向分辨率高等显著优势，被广泛应用于隐伏岩浆岩及断层探测，俯冲带、大陆裂谷、岩墙群及地幔柱等构造特征分析，磁性界面（包含结晶基底及居里等温面）反演，区域构造划分以及孕震构造背景研究等领域. 近来随着航空磁测技术的发展，积累了越来越多大比例尺、高精度的航磁数据，并在此基础上产生了新的全球/区域地壳磁异常图/模型. 在由航磁异常对场源位置、形态、走向及埋深等进行分析反演方面，人们使用了化极、延拓、求导（包含水平及垂向导数、斜导数、总水平导数、总梯度模及各类导数组合）、欧拉反褶积、磁性界面及磁化率反演等多种技术. 本文对岩石磁性和磁异常解释的不确定性进行了整理和归纳，对各种航磁异常分析及反演技术进行了介绍，对航磁异常在不同场景下的地质构造应用进行了回顾，并对未来航磁探测、数据分析及应用等发展进行了讨论和展望.Abstract: Aeromagnetic anomaly has the obvious advantages of wide coverage, low cost and high lateral resolution in geological structure research, and has been widely used in concealed magmatic rock and faults detection, tectonic characteristics (e.g. subduction zone, continental rift, dike swarm and mantle plume) analysis, magnetic interfaces (including crystalline basement and Curie Point Depth) inversion, regional tectonic division and study on seismogenic tectonic background. Recently, with the rapid development of aeromagnetic survey technology, more and more high-precision and high-resolution aeromagnetic data have been accumulated, and new global/regional aeromagnetic anomaly maps/models have been generated on this basis. In analyzing and inverting the position, shape, trend and buried depth of field source from aeromagnetic anomaly, various boundary identification techniques such as reduction to the pole, upward continuation, derivations (including vertical and horizontal derivative, oblique derivative, analytic signal amplitude and combinations of derivatives), Euler deconvolution and magnetic boundaries or magnetic susceptibility inversion have been developed. This paper organizes and summarizes rock magnetism and uncertainty of interpretation of magnetic anomalies, introduces various magnetic data analysis and inversion methods, reviews the geological and tectonic applications in different aspects, and discusses and prospects the development of aeromagnetic detection, data analysis and tectonic application in the future. As the basis of aeromagnetic anomaly interpretation, the characteristics of susceptibility of rocks are summarized as follows: the susceptibility of minerals is positively correlated with their iron content. Rock susceptibility is mainly determined by the less abundant content of ferromagnetic minerals (mainly magnetite). The current susceptibility measurements are still not representative enough, thus more in-situ detections especially deep rock samplings are in need and three-dimensional susceptibility models of the continental lithosphere need to be established in the future. In the interpretation of aeromagnetic anomalies, attentions should be paid to the influence of uncertainties, which include non-uniqueness of the inverse problem, annulator, demagnetization, field-source superposition and induced-remanent magnetization separation. For various boundary recognition and inversion techniques to detect the location and buried depth of magnetic sources by aeromagnetic anomalies, it is necessary to be familiar with the advantages and limitations of each technique, and select them according to different research objectives. For example, vertical derivative can be used to identify the center of the source, horizontal derivative can be used to identify the boundary, and oblique derivative can be effectively used to identify the deep source. When magnetic anomaly analysis is applied in geological structure study, appropriate means should be selected according to specific structural problems. For example, to detect concealed magmatic rocks or concealed faults near the surface, the first-order vertical derivative or total horizontal derivative analysis can be used. For the buried depth of rock or the deep distribution of fault zone, qualitative analysis of upward continuation, semi-quantitative analysis of Euler deconvolution and quantitative analysis of three-dimensional magnetic susceptibility inversion can be applied.
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Key words:
- aeromagnetic anomaly /
- geology /
- tectonics /
- analysis /
- inversion
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图 1 龙门山断裂带附近10 km高度处的化极磁异常（左）及θ图（右）分布
Figure 1. The RTP ∆T （Left） and θ-map （Right） distribution around Longmenshan fault belt at an altitude of 10 km
图 6 龙门山断裂带两侧基底分布特征示意图（修改自Lei et al., 2022）
Figure 6. Schematic diagram of basement distribution on both sides of Longmenshan fault zone (modified from Lei et al., 2022)
图 2 细剖分法（Dipole100）、偶极子近似法（Dipole）、泰勒级数展开法（TSP）和高斯—勒让德积分法（GL5×5×5）计算的磁异常Bx曲线分布图. 观测点位于20 km高度
Figure 2. Calculated distribution of magnetic anomaly Bx by: Subdivision (Dipole 100), Dipole approximation (Dipole), Taylor Series exPansion (TSP) and Gause-Legende integral (GL5×5×5) methods. The observation points are located at an altitude of 20 km
图 3 雅鲁藏布江缝合带中部两条磁异常条带深部岩性成因示意图 （修改自Wang et al., 2020a）
Figure 3. Schematic diagram of deep lithologic genesis of the two magnetic anomaly bands in the middle of Yarlung Zangbo Suture zone (modified from Wang et al., 2020a)
图 4 南西奈塔巴地区航磁解析信号振幅（左）及斜导数总水平导数（右）同断层分布（修改自Khalil, 2016）
Figure 4. Comparison of the analytical signal amplitude (left) and the total horizontal derivative of the tilt derivative (TDR_THD)(right) with faults at Taba, South Sinai (modified from Khalil, 2016)
图 5 （a）塔里木盆地磁异常解析信号振幅分布；（b）径向信号异常特写；（c）由磁异常勾画出地幔柱原始形态；（d）新生代变形恢复（修改自Xu et al., 2020）
Figure 5. (a) Analytical signal of aeromagnetic anomalies in the Tarim Basin；(b) Close-up distribution of radial signal anomalies； (c) Original morphology of imaged plume；(d) Restoration of Cenozoic deformation (modified from Xu et al., 2020)
图 7 全球居里面分布参考模型 （Li et al., 2017）
Figure 7. Global reference Curie point depth model (Li et al., 2017)
图 8 基于航磁数据得到的中国大陆区域地质构造图 （修改自Xiong et al., 2016a）
Figure 8. Regional geotectonic map of continental China based on aeromagnetic data (modified from Xiong et al., 2016a)
图 9 由航磁异常推测孕震断层展布. （a）三维磁化率反演结果；（b）磁化率剖面；（c）由航磁、重力及DInSAR得到的地震地质构造背景解释；（d）剖面构造概念图 （修改自Kolawole et al., 2017）
Figure 9. Seismogenic faults distribution deduced from aeromagnetic anomalies. (a) Inverted 3D mangetic susceptibility. (b) Susceptibility profile. (c) Interpretation of geotectonic setting of earthquakes based on DInSAR, aeromagnetic and gravity data. (d) Conceptual 2D tectonics of the cross section (modified from Kolawole et al., 2017)
表 1 常见矿物体积磁化率数值范围 （修改自Hunt et al., 1995; Dunlop and Özdemir, 2007）
Table 1. Numerical range of volume magnetic susceptibility of common minerals (modified from Hunt et al., 1995; Dunlop and Özdemir, 2007)
磁性种类 矿物名称 矿物化学式 Fe质量百分比/% 体积磁化率/（×10−3SI） 颜色 主/次 抗磁性 石英 SiO2 0 −16.4×10−3 浅色矿物 主要矿物 长石 KAlSi3O8 0 −14.9×10−3 方解石 CaCO3 0 −13.6×10−3 顺磁性 黑云母 KR3AlSi3O10OH2* <31 0.5~1.15 暗色矿物 角闪石 Fe7Si8O22OH2 <37 0.5~2.7 辉石 R2Si2O6* <40 1.55~1.8 橄榄石 R2SiO4* <53 1.56~5.53 钛铁矿 FeTiO3 37 4.7~5.2 次要矿物 赤铁矿 Fe2O3 70 0.5~40 黄铁矿 FeS2 46.7 1.5 铁磁性
（亚铁磁性）铁 Fe 100 3.9×103 磁铁矿 Fe3O4 72.4 3.0×103 磁赤铁矿 Fe2O3 70 2.0~2.5×103 磁黄铁矿 Fe7S8 60 3.2×103 钛磁铁矿 0.13~0.62×103 * R代表可能被Fe元素或其它元素占据的晶格位置. 
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表 2 常见岩石类型体积磁化率数值范围（修改自Hunt et al., 1995; Clark, 1999; Dunlop and Özdemir, 2007）
Table 2. Numerical range of volume magnetic susceptibility of common rocks (modified from Hunt et al., 1995; Clark, 1999; Dunlop and Özdemir, 2007)
岩石种类 主要矿物 体积磁化率（×10−3SI） 岩浆岩 超基性 橄榄岩 橄榄石 96~200 基性 辉长岩 辉石 1~160 玄武岩 0.25~180 中性 闪长岩 角闪石、黑云母、长石 0.63~130 安山岩 170 酸性 花岗岩 黑云母、长石、石英 0~50 流纹岩 0.25~38 沉积岩 碎屑沉积 砂岩 长石、石英 0~20.9 页岩 0.063~18.6 化学沉积 灰岩 方解石 0~25 白云岩 方解石 −0.01~0.94
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